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RECORD 1989/35

AUSTRALIAN PHANEROZOICTIMES CALES

5. CARBONIFEROUS

BIOSTRATIGRAPHIC CHARTS AND EXPLANATORY NOTES

• by

P.J. JONES

BUREAU OF MINERAL RESOURCES, GEOLOGY AND GEOPHYSICS

I^11 1^11* R 8 9 0 3 5 0 1 *

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Refer to this publication as:-^ •

JONES, P.J., 1991.^Australian Phanerozoic Timescales:^5. Carboniferous.Biostratigraphic charts and explanatory notes. Bureau of Mineral Resources, Australia,Record 1989/35.^ •

•© Commonwealth of Australia, 1991 •This work is copyright. Apart from any fair dealing for the purposes of study, research,criticism or review, as permitted under the Copyright Act, no part may be reproducedby any process without the written permission of the Director, Bureau of MineralResources, Geology and Geophysics. Inquiries should be directed to the PrincipalInformation Officer, BMR, GPO Box 378, Canberra, ACT 2601. •

COVER ILLUSTRATION: Xystridura milesi (Chapman, 1929) from the early MiddleCambrian, Beetle Creek Formation, Mount Isa district, Queensland.

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•^FOREWORD

A time framework is essential to an understanding of all historical aspects of the geosphere. It is aprerequisite to interpreting the development and structure of the sedimentary basins which host our majorpetroleum, coal, and sedimentary mineral deposits, and is important when seeking patterns in the distributionof these resources through time. It is also critical to our understanding of the interactive factors which haveshaped the modern Australian environment, and in determining the patterns of global change.

For the Phanerozoic (the last 570 million years, the period of 'visible life), the most efficient way ofestablishing such a time framework is by the study of fossils (palaeontology), and their stratigraphicdistribution (biostratigraphy).

Early palaeontological investigations of Australian sedimentary basins were used during the nineteenthcentury to establish the age of major suites of sedimentary rocks. This provided a framework for theapplication of more detailed biostratigraphic research, an early example being the use of graptolites tosubdivide Ordovician strata in the Victorian goldfields at the beginning of this century. The Victoriansequence of graptolite zones is the current standard used throughout Australasia, and is one of the mostfinely subdivided in the world.

The development of Australian biostratigraphy over the last 50 years has provided many biostratigraphicschemes using the fossil remains of a wide range of organisms - from the microscopic (such as pollen grainsand spores of land plants), to the macro- and megascopic (such as larger invertebrates, fish, mammals, evenhuman artifacts). Recent years have also seen a rapid growth in other methods of measuring geological time,using radioactive decay of mineral elements, or reversals in the Earth's magnetic field. These provide ameans of calibrating biostratigraphic schemes with a numerical time scale.

The current Phanerozoic Timescales Series makes available for immediate use a prellininary set of chartsbased both on recent palaeontological data from the specialist scientific literature, and unpublishedinformation from ongoing biostratigraphic research. The charts integrate, for each geological period, zonalschemes using different groups of fossils with isotopic and other data (magnetic reversal, eustasy curves), andshow the relationship of the Australian zones to standard international timescales and their numericalcalibration, where this information is available. Inevitably the detail of treatment and reliability varies fordifferent parts of the column, and for different groups of fossils, and much work still needs to be done todevelop a fully integrated chronological scale comparable to those available in the Northern Hemisphere.The current series is made available to provide a set of up-to-date calibrated biostratigraphic chartsspecifically for use in the Australasian region.

Biostratigraphic charts were initially prepared for the AMIRA (Australian Mineral Industries ResearchAssociation) sponsored Palaeogeographic Atlas of Australia project. The current charts and explanatory texthave been revised and updated as part of the second phase of that project, the Phanerozoic History ofAustralia, which is funded in part by APIRA (Australian Petroleum Industry Research Association). Thecharts have been compiled by palaeontologists in BMR, but incorporate contributions by other specialistsworking in State Geological Surveys, universities and the exploration industry, without which such acomprehensive compilation would not have been possible.

J. H. ShergoldHead of ProgramOnshore Sedimentary & Petroleum Geology Branch

CONTENTS

•INTRODUCTION^ 1

PURPOSE AND SCOPE OF STUDY ^ 1HISTORY OF THE CARBONIFEROUS SYSTEM . 2CARBONIFEROUS BIOCHRONOLOGY . . . . ....THE CARBONIFEROUS SYSTEM, ITS LIMITS

3 •AND SUBDIVISIONS ^ 3

AUSTRALIAN CARBONIFEROUS ^ 5

GEOCHRONOLOGY^ 7 •AUSTRALIAN BIOCHRONOLOGY ^ 10

1.^KEY GROUPS ^ 11Brachiopods ^ 11Conodonts ^ 13Mollusca (ammonoids) ^ 15Ostracods ^ 17Microfloras ^ 17

2.^OTHER GROUPS^ 18Conchostraca ^ 18Corals ^ 18Foraminiferida and algae ^ 18Mollusca (Bivalvia, Gastropoda) ^ 19Radiolaria ^ 19 •Trilobites ^ 19Vertebrates ^ 20

ACKNOWLEDGEMENTS ^ 20

REFERENCES ^ 21

CAPTIONS FOR CHARTS 1-3 ^ 42

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INTRODUCTION

Purpose and scope of study

Two biostratigraphic schemes showing correlations of Carboniferous rocks thr­oughout the Australian continent have appeared in the past 18 years. The first, published by the Bureau of Mineral Resources (Jones et aI., 1973), was a chart with accompanying notes that attempted to correlate the Australian sequences in terms of the western Euro­pean succession on the basis of the evidence from the marine invertebrate faunas (mainly from ammonoids, and to a lesser extent from brachiopods and conodonts). The second, published by the lUGS (Roberts, 1985a), was a more detailed account of Australian Carbonif­erous geology, which summarised new published data on the marine invert­ebrate faunas (brachiopod, ammonoid, conodont, trilobite), and the palynofloral and floral successions, and as a conseq­uence, revisions to previously published correlations.

Biostratigraphic results of subsequent palaeontological publications have been incorporated in working biostratigraphic charts as they became available, to main­tain an up-to-date biochronological database. An earlier abbreviated sum­mary using this biostratigraphic informa­tion for the Carboniferous was prepared in 1987 as a chart for the BMR/ APIRA Palaeogeographic Maps Project, to provide biostratigraphic control for the Carboniferous correlation charts (see Totterdell, Brakel & Jones, in prep.).

Three new charts are provided with the present review, which update previous syntheses. Chart 1 shows correlations between the biochronologic and geochr­onologic scales of Australia and Carbon-

CARBONIFEROUS 1

iferous stratigraphic subdivisions of west­ern Europe, the Soviet Union, the USA (columns 2-6), South China and Argentina (columns 19-22). Selected biozonal schemes supporting correlations between these key areas are summarised in columns 7-13 (ammonoids, forams, conodonts, megaflora and microflora). Summary columns for key fossil groups used in biostratigraphic zonation of the Australian Carboniferous (conodonts, forams, brachiopods, ostracods, microflo­ra) are given in columns 14-18 of this chart.

Conodonts are now the most widely used key group for international correlation, and Chart 2 shows vanous zonal schemes in current use. The Australian Carboniferous conodont zonation is based on an integration of schemes from the Bonaparte and Canning Basins in W A with the results of a recently completed zonation for eastern Australia. The eastern Australian zonation is more readily correlated with conodont zonations from North America, and the latter are summarised on the right side of Chart 2. The western Australian zonation can be tied in (with some difficulty) to conodont zonations from western Europe, which are summarised on the left side of the chart. The chart incorporates the latest published work, including a recent taxonomic and biostratigraphic analysis by Jenkins et al. (in press) on Visean conodonts from eastern Australia.

The ammonoid faunas from eastern Australia have in the past been used to control the correlation of Australian brachiopod zones, but results of recent conodont studies indicate problems with the resulting ages (e.g. Jenkins, 1974). Chart 3 shows the most recent conodont zonation for the Early Carboniferous

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•(Dinantian) of eastern Australia againstMamet's foraminiferal zonation. Thesegroups have been used to calibrate theeastern Australian Carboniferousbrachiopod zonation presented in column5. A summary of the biostratigraphicdistributions of all named EarlyCarboniferous (Dinantian) Australianammonoid species is shown on the rightof the chart. For comparison, thestandard ammonoid scale andstratigraphic subdivision for theDinantian of western Europe are shownin columns 1 and 2.

History of the Carboniferous System

The concept of the Carboniferous as aset of stratigraphically related rocks hasits origin in the early nineteenth centuryof western Europe (Brinkmann, 1960;Ramsbottom, 1984). In 1808 J.B.Omalius d'Halloy recognised a unionbetween the productive coal measures(his 'terrain houiller') and the limestonebeds below. However, the termCarboniferous, the earliest of themodern System names to be proposed,was first used as a stratigraphical term byRev. W.D. Conybeare (1787-1857) &William Phillips (1773-1828) in theirbook on the 'Outlines of the Geology ofEngland and Wales', published in May,1822. The authors included within theCarboniferous, the "Coal-measures, Car-boniferous limestone, and Old red sands-tone" of England and Wales, butknowing that William Smith hadproduced a geological map on the basisof fossils seven years (1815) earlier, theyexpected the Carboniferous would bewidely recognisable by its distinctivefossils rather than its lithology.

John Phillips (1835) first used the combi-nation 'Carboniferous System', onemonth after Murchison (1835) apparently

first used the word System as a formalstratigraphical term in relation to theSilurian. The Old Red Sandstone waslater removed from the Carboniferous,when the Devonian System was proposedin 1839, after it was realised (largely dueto the fossil studies of William Lonsdale)that it is the lateral continental-faciesequivalent of the marine (Devonian)rocks of Devonshire.

Soon after John Phillips started todescribe the rich fauna of theCarboniferous Limestone in England,McCoy commenced similar work inIreland, and L. de Koninck began inBelgium. The coal measures, readilyidentifiable by their distinctive fossilflora, were recognised in coal basins ofwestern Europe (Britain, France, Belg-ium, Germany) and eastwards into theSilesian coalfield of Poland, and theDonetz Basin of Russia. They were alsorecognised westwards in the coal basinsof Nova Scotia, Canada, and in theAppalachian coalfields of the USA.

Although the term Carboniferous haspersisted in Europe (and Australia) tothe present day, it was replaced in theUSA (and to some extent in Canada) bythe two-fold division Mississippian (forthe lower part) and Pennsylvanian (forthe upper part) by the end of thenineteenth century. Winchell (1872) firstintroduced the term Mississippian for thesequence that overlies the Devonianstrata and underlies the "Coal Measures",now called the Pennsylvanian System.Williams (1891: 136) quoted Winchell(1872) as stating the proposal for ".... theuse of the name Mississippi limestoneseries or Mississippi group as ageographical designation for the Car-boniferous limestones .... which are solargely developed in the valley of theMississippi River." The type area is

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named from exposures in the bluffs of the upper Mississippi River valley from Iowa to southern Missouri. The name Pennsylvanian Series was introduced by Williams (1891: 83) who designated the "upper Carboniferous" coalfields in the northern Appalachian area, in Pennsylvania, as the type area. The type succession ranged from the base of the "Millstone grit" or Pottsville "formation" to the top of the "Upper Barren Coal Measures" or Dunkard "formation".

Carboniferous biochronology

Over 170 years of palaeontological research on Carboniferous fossils has led to the development of three principal standard stratigraphic scales for the Carboniferous - western Europe, the United States, and the Soviet Union (see Chart 1). During this time research into Carboniferous biochronology resulted in great advances in the correlation of these scales, using mainly marine invertebrate macrofossils goniatites in rocks deposited in open marine environments, and freshwater bivalves in non-marine rocks. For many years the sequence of German goniatite zones was used as a standard for the correlation of the Lower Carboniferous. It was not until the early 1970's with the advent of detailed conodont biostratigraphy (Matthews, 1970; Weyer, 1972) that it was realised that the German ammonoid sequence is not sequential or contiguous. Over the last 20 years the use of various microfossil groups, particularly conodonts, foraminifera (fusulinids) and spores, have greatly refined the correlation of Carboniferous strata throughout the world, although many problems in international and regional correlation remain to be overcome.

CARBONIFEROUS 3

The Carboniferous System, its limits and subdivisions

Devonian-Carboniferous boundaIy and the base of the Carboniferous

The Carboniferous Congress at Heerlen in 1935 defined the base of the Carbonif­erous at the entry of the goniatite species Gattendorfia subinvoluta and the base of the Gattendorfia Genus Zone (or Stufe) within a reference section in· the Oberroedinghausen railway cutting at Hoennetal, Sauerland (Jongmans & Gothan, 1937). This decision subsequently lacked international agreement, as French speaking countries and the USSR continued to use a lower boundary at the base of the Strunian, near the base of the Wocklumena Genus Zone.

The subsequent use of conodonts and spores, which are more wigespread than goniatites, led to pressure for a redefinition of the Devonian Carboniferous boundary. In 1979, a decision was made to recommend an operational boundary using the first appearance of the conodont Siphonodella sulcata within the evolutionary lineage from S. praesulcata to S. sulcata. This level is slightly below the lowermost record of Gattendorfia subinvoluta in the Hoennetal section (Paproth, 1980).

The La Serre section in the Montagne Noire (Flajs & Feist, 1988) is now the accepted and ratified Global Boundary Stratotype and Point (GBSP), with the boundary being taken at the base of bed 89 of that section. Auxiliary boundary stratotypes are at Hasselbachtal (west Germany; Becker et al., 1984; Becker, 1988) and Nanbiancum (south China; Yu, 1988) ..

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Carboniferous-Permian boundary

The position of the upper limit of theCarboniferous has yet to be decided bythe International Carboniferous/PermianWorking Group. Over the past five yearsthere have been several conflicting opin-ions as to where this boundary should beplaced. The traditional view is to place itat the base of the PseudoschwagerinaZone, at the base of the Asselian Stage,the Soviet boundary stratotype for thebase of the Permian System in the Urals.Other opinions would have this boundaryas high as the top of the Maping Seriesof China, at the first appearance of thefusulinid Pamiria, which would correlatewith the base of the Sakmarian Stage ofthe Urals section, and as low as the baseof the Maping Series, at the base of theMontiparus (or Obsoletes) Zone (Zhang,1987), which would correlate with thebase of the ICasimovian Stage of theSoviet standard-section, the base of theMissourian Stage of the USA, and thebase of the Stephanian Series of westernEurope.

Recent detailed studies in the Urals (e.g.Davydov & Popov, 1986; Popov & Davy-dov, 1987) and in South China (WangZhi-hao, 1991) favour the traditionalview. It should be noted that a newfusulinid zone (Zone of Daixinabosbytauensis- D. robusta) has beendistinguished between the zones ofDaixina sokensis and Sphaeroschwagerinavulgaris- S. fustformis (Davydov, 1984,1988); this new zone is not shown inChart 1.

The Commission on the Permian Systemof the Interdepartmental StratigraphicCommittee of the USSR decided (June,1990) to draw the Carboniferous-Permian boundary (and therefore thelower boundary of the .Asselian) on the

basis of the goniatite scale between thegenozones Shumardites-Vidrioceras andSvetlanoceras-Juresanites. In the fusulinidscale this boundary is drawn between thezones of Daixina bosbytauensis-D. robustaand Sphaeroschwagerina vulgaris- S.fustformis (sensu stricto). This boundaryin terms of the conodont succession(Chernykh & Reshetkova, 1987)corresponds to the major evolutionarychange from Streptognathoduswabaunsensis to S. barskovi, and is equiv-alent to the base of the S. barskovi Zonein both the Urals and South China(Wang Zhi-hao, 1991).

In western European terms the Carbon-iferous/Permian boundary may be takenat the Stephanian/Autunian boundary(sensu Bouroz & Doubinger, 1977).These authors showed on palynologicalevidence (Bouroz & Doubinger, 1977;Doubinger & Bouroz, 1984) that thebase of the Asselian lies within the lowerAutunian at the base of the Assise deMuse. The Assise d'Igornay of thelowermost Autunian, below theCarboniferous/Permian boundary, wasthen referred to the Stephanian (asStephanian D). Wagner (1984) arguedagainst this redefinition, because a newbase of the Autunian was proposed inthe type locality solely for the purpose ofcorrelation with the Carboniferous-Permian boundary in the Sovietstratotype (cf. Rotai, 1979).

Important boundaries within theCarboniferous System

Although the use of a two-foldsubdivision of the Carboniferous waswell established in western Europe andNorth America, a three-fold division (asseries) continued to be used in theUSSR. An attempt to integrate the twoschemes was suggested by Bouroz et al.

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(1978) and Rotai (1979), which placedthe Upper, Middle, and Lower Series ofthe Russian Carboniferous within thetwo-fold Mississippian and PennsylvanianSubsystems of North America. Howeverthere is still much discussion concerningthe fixing of the Lower-UpperCarboniferous Subsystem boundary, andthe fact that the western Europeansubsystem boundary between the Silesianand Dinantian does not coincide with theMississippian/Pennsylvanianboundary ofthe North American scheme. In view ofthe present uncertainty of globalcorrelations about the mid-Carboniferous

• boundary (see Lane et al 1985; Lane &Ziegler, 1985), it seems premature to usean international standard schemecombining elements of American,Russian and west European standards in

• a single scale, such as Bouroz et al.(1978) have done. The present reviewretains these separate schemes (seeChart 1).

• A second problem concerns the recogni-tion and correlation of the Tourna-isian-Visean boundary, a subject of somecontroversy (e.g., Conil in Conil et al.,1969: 40-45: versus Mamet et al., 1970:

• 33-37). However, as ratified by the Sub-commission of CarboniferousStratigraphy (Conil, 1969: 188-9; Mametin George & Wagner, 1972: 146), theTournaisian-Visean boundary lies 34 mbelow the conventional base of theMarbre Noir de Dinant of the CarteGeologique de Belgique, and it islocated precisely at the base of Bed 141of the boundary stratotype section atDinant (see Conil et al., 1969). Lane &Ziegler (1983) and Belka & Groessens(1986) have discussed in detail the cono-dont succession around the boundary inthat section. Lane & Ziegler (1983),using data from Conil et al. (1969),correlated the Tournaisian-Visean

boundary with the preliminary standardconodont zonation, and placed it withinthe anchoralis Zone. The same sectionalso has an important bearing on thedistribution of Mamet's foraminiferalzones about the Tournaisian-Viseanboundary (Sohn & Jones, 1984: 69). Theposition of the boundary, as ratified bythe SCCS, means that the base of theVisean (Via = "Sovet" OBJ.) lies withinMamet's Zone 9, and that V1b of Conil(i.e., Via Marbre Noir de Dinant, plusV1b Sovet) contains both Mamet's Zones10 and 11. Its position correspondsapproximately with the base of the Ger-man goniatite zone CuII-y. The basis forthe recognition of this horizon inAustralia is discussed below.

Recently Conil et al. (1989) have shownthat the base of the Belgian stage(Moliniacian) formally taken to be thebase of the Visean in fact lies, bycorrelation with the boundary stratotypesection at Dinant, within theTournaisian. This recent result has notbeen incorporated in the present charts.Riley (1990b; 1991) has also discussedthis question from the point of view of ofthe British Chadian stage, which heregarded as mainly Tournaisian.

The base of the Namurian is taken asthe base of the range zone ofCravenoceras leion, following the HeerlenCongress decision of 1958. Horn (1960)has shown this zone to overlap the upperpart of the German goniatite zone Cull!/, viz., Cull! /2, which had previouslybeen considered as the latest unit in theVisean.

Australian Carboniferous

The first Carboniferous fossils fromAustralia were collected by Strzeleckifrom the Booral district, in the Hunter

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Valley of the Colony of New SouthWales in late 1842. The following yearhe took them to England, and donatedthem to the British Museum (NaturalHistory) London, where they weredescribed by Morris (in Strzelecki, 1845).Morris described two species ofgastropods, one ostracod (Bairdia affinis;the first ostracod species to be describedfrom Australia), one brachiopod species,and some fish remains ("an Icthyo-dorulite"), a fauna which, in present dayterms, probably came from the Levip-ustula levis Zone of the BooralFormation (Campbell, 1955, 1961).

Two years after Strzelecki's report,McCoy (1847) described some of theRev. W.B. Clarke's extensive collectionsof brachiopods, corals, and trilobitesfrom the Hunter Valley. De Koninck(1877) described other of Clarke'scollections, and both palaeontologistscompared them with LowerCarboniferous species from Europe.Systematic descriptions of Carboniferousfaunas of eastern Australia continuedwith such authors as Jack & Etheridge(1892), Dun (1902), Dun & Benson(1920), Carey (1937), Carey & Browne(1938), and Delepine (1941).

Recognition of authentic Carboniferousrocks in Western Australia came muchlater than in the east. They were firstdiscovered in 1945 in the Burt Range ofthe Bonaparte Basin (Matheson &Teichert, 1948), and in 1949 they werefound in the Carnarvon Basin (Teichert,1950). Carboniferous rocks werediscovered in the Canning Basin in 1955in subsurface, and in 1956 in outcrop(Thomas, 1957; 1959). Howevererroneous Carboniferous records in thisbasin date back to Hardman (1884, 1885)and Blatchford (1927).

According to current understanding therewere two distinct regions of mainlymarine sedimentation during theCarboniferous in Australia: a region ofintracratonic basins, mostly in thewestern part of the present continent,and a region within the Tasman MobileBelt, covering the eastern margin (seeJones et al., 1973). Detailed correlationbetween the two regions has beenlimited by differences in the compositionof the faunas, as discussed below. A thirdregion, of dominantly terrestrial sedimen-tation and characterised by the scarcityof marine fossils, is represented in thecentral part of the continent (e.g.Amadeus and Ngalia Basins).

There are no formally designated localstages for the Carboniferous of Australia.The brachiopod zones of easternAustralia (Roberts, 1975) were groupedinto three major faunal divisions(Werrian, Gresfordian, andBarringtonian) by Jones & Roberts(1976), which could form the basis oflocal stages in the future, and Clarke &Farmer (1976) proposed the Hellyerianfor the Stage 1 microflora (Kemp et al.,1977) in Tasmania, but none of theseunits has formally designated boundarystratotypes. In the absence of formallydesignated local stages, there are threeareas that provide standard stratigraphicscales with which to compare theAustralian Carboniferous - westernEurope, Soviet Union, and USA.

The western European scale is the mostappropriate standard for the Carbonifer-ous of Australia, where cosmopolitanshelly faunas of the Early Carboniferous(Dinantian) are replaced by endemic(Gondwanan), poorly-represented faunasof Late Carboniferous (Silesian) age(Druce & Jones, 1974). It is also thescale favoured most by Australian

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palynostratigraphers (e.g. Helby &Playford in Kemp et al, 1977; Powis,1984). Powis (1984) used the westEuropean scale "because resolution tothe USSR stage level using palpology, isnot possible with a high degree ofconfidence in Australia." As noted above,the present uncertainties regardingglobal correlations about themid-Carboniferous boundary (see Lane

• & Ziegler, 1985) preclude adoption of aninternational standard scheme, like thatproposed by Bouroz et al. (1978) to com-bine elements of American, Russian andwest European standards in a single

• scale. The scarcity of conodonts and theabsence of fusulinid foraminiferids in thelate Carboniferous (Gondwanan) faunasof Australia inhibit their correlation withthe standard sequences of North

flt America and Russia, where the mainbiozonations are based on these groups.

The Devonian/Carboniferous boundaryin Australia is taken at the Wocklum-

• erian/Balvian boundary of Germany,which is close to the Strunian/Hastarianboundary of Belgium. The standardstratigraphic scale for the AustralianCarboniferous used in Chart 1 is a

• compilation of scales proposed by severalauthors for western Europe (George etal., 1976 and Paproth et al., 1983 for theDinantian; Ramsbottom et al., 1978,Owens et al., 1985, and Wagner &Winkler Prins, 1985 for the Silesian).

GEOCHRONOLOGY

The geochronologic scale used for Chart1 (column 1) brackets the CarboniferousSystem between 354 Ma and 295 Ma.These dates were compiled from areview of recent literature, and wereadopted as a best compromise to complywith the numeric ages previously used

• for the Devonian and Permian timescales

already produced (Young, 1989;Archbold & Dickins, 1991). It should benoted however that recent work byClaoue-Long et al. (in press) has furtherrefined the Devonian-Carboniferous dateto 353.2 ±4 Ma.

Earlier estimates approximating this datein recent literature were all based on oldisotopic results, or data which were verypoorly constrained biostratigraphically.Examples are the 354( + 10-5) Ma figuresuggested by McKerrow et al. (1985), the356±66 Ma and 357±66 Ma computationsderived by Carr et al. (1984), and the357 Ma age interpolated by Bayer &McGhee (1986) based on cyclic patternsin the Devonian. In contrast to thesedates, Forster & Warrington (1985)proposed a 365±55 Ma date for theDevonian/Carboniferous boundary,based on radiometric data available fromthe Scottish Borders (De Souza, 1982)and from eastern Victoria (Richards &Singleton, 1982; Williams et al, 1982).

Regarding the biostratigraphicconstraints on these isotopic dates, it isnoted here that the base of theCarboniferous cannot be picked withprecision in the red bed sequences of theScottish Borders or those of Victoria,because marine fossils are absent andplant miospores have not beenpreserved. In the zonation of the LowerCarboniferous based on miospore assem-blages (Neves et al., 1973), the basal twozones recognized in England (PL, nowlatest Devonian, and NV) have not beenfound in Scotland or the ScottishBorderlands. Here, the lowest zone (CMZone) of late Courceyan age (Clayton,1985) conformably overlies Upper OldRed Sandstone, which suggests that theOld Red Sandstone facies extendsupwards into the Carboniferous. Asimilar situation exists at Cultra, County

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Down, Northern Ireland (Clayton, 1986).In the Scottish Border region, theBirrenswark and Kelso lavas, with amaximum K/Ar average age of 361+ 7Ma (De Souza, 1982) are used locally toarbitrarily define the base of theCarboniferous (House et al., 1977). Thelavas immediately overlie calcretepalaeosols formed at the top of UpperOld Red Sandstone sediments (Leeder,1976). The Whita Sandstone, thatdirectly overlies the Birrenswark Lava, isdifficult to correlate with neighbouringdated sequences, because of the lack ofmarine fossils. The same may be said ofthe Cementstone Group that overlies theKelso Lava. Both lavas must be regardedas dubious time-markers, because similarlavas have been found in bore holematerial, well down in the Upper OldRed Sandstone (Westoll, in House et al.,1977: 71). Thus, the stratigraphical ageof the Scottish Border lavas is an openquestion, as apparently there are nodefinite arguments which reject a latestDevonian stratigraphical age (Odin,1985b: 116).

Regarding the Victorian sequence Odin(1985b) pointed out that the youngestlimit proposed by Forster & Warrington(1985) is older than the date accepted bythe authors of the original studies inVictoria i.e., both Richards & Singleton(1982) and Williams et al., (1982) pro-posed a Devonian/Carboniferousboundary younger than 360 Ma. Thedated granites of eastern Victoria (e.g.the Barjarg and Strathbogie Granites)with an overall mean age of 360±1 Ma(Richards & Singleton 1981: 405, 417)intrude the Cerberean Volcanics (aminimum 367±2 Ma for the pre-lateFrasnian; Williams et al., 1982), and arethemselves unconformably overlain bythe Mansfield Group. Hills (1936) placedthe Devonian/Carboniferous boundary

arbitrarily at the base of the MansfieldGroup. The Broken River fish fauna inthe middle part of the Mansfield Groupat present indicates a generalCarboniferous age (J.A. Long, fide G.C.Young), and therefore cannot be used asevidence to suggest that the non-volcanicred beds in the lower part are of possibleLate Devonian age. However, thestratigraphic position of the Devonianfish faunas indicate that volcanicityceased in eastern Victoria well beforethe end of the Late Devonian, allowingtime for flood-plain red bedsedimentation (Marsden, 1976: 109).Thus, the Victorian evidence indicates aDevonian/Carboniferous boundaryyounger than 360 Ma, which may lieabove the base of the Mansfield Group.This evidence is consistent with the newdate of 353.2 + 4 Ma for the Devonian-Carboniferous boundary based on recentwork in the German stratotype sectionusing the SHRIMP ion microprobe (Cla-oue-Long et al., in press).

Previously the Tournaisian/Viseanboundary in Australia has been taken atabout 342 Ma on the basis of the oldestdated volcanic in the succession of thesouthern New England Orogen (Jones,1988; also used by Cowie & Bassett,1989 for the IUGS Global StratigraphicChart). The unnamed pyroxene andesitein the upper part of the WaverleyFormation, near Foybrook, previouslydetermined to have a K/Ar age of341 +4 Ma (see Jones, 1988), is nowknown to be considerably older, andrevisions to stratigraphy suggest it is notan apppropriate datum for determiningthe Tournaisian/Visean boundary (cf.earlier discussion by Jones, 1988). Partlyon the basis of new and unpublishedwork, the Tournaisian/Visean boundaryon the charts is now estimated at about345 Ma.

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As previously noted (Jones, 1988), the355±55 Ma proposed by De Souza (1982)for the Tournaisian/Visean boundary inthe Midland Valley of Scotland is too oldby comparison with the Australian evid-ence, and is more likely to correspond tothe Devonian-Carboniferous boundary(see above). The validity of the Scottishradiometric dates has also been ques-tioned on the evidence of palynologicalcorrelation of the early Carboniferous ofthe Midland Valley (see Paterson &Hall, 1986: 8).

The 325-326 Ma date suggested byLippolt & Hess (1985) and Hess &Lippolt (1986) and Forster & Warrington(1985) for the Visean/Namurianboundary is compatible with Australianisotopic age data (Roberts & Engel,1980). In contrast, the 333 Ma datesuggested by Harland et al. (1982, 1990)for the Visean/Namurian boundary istoo old, when compared with the easternAustralian evidence. The average age of331 Ma quoted for the Martins Creek

Ignimbrite of the Hunter Valley (e.g.Roberts & Engel, 1980) has been revisedto 334.2 ±1.8 Ma (Claoue-Long, Jones &Truswell, 1989). This ignimbrite liesbetween the Linoprotonia tenuirugosusSubzone, the upper Subzone of theDelepinea aspinosa Zone and the Rhipid-omella fortimuscula Zone. Previously theammonoids of the fortimuscula Zonewere regarded as Brigantian age(Campbell, Brown & Coleman, 1983).However recent conodont work (Jenkins,Mory & Crane, in press) demonstratesthat the fortimuscula-aspinosa zoneboundary lies within the Holkerian (seeChart 3). Thus, the mid-Holkerian canbe dated at 334.2 ±1.8 Ma, an age rangewithin the 335 Ma for the base of theAsbian as estimated by De Souza (1982).In this review, an estimate of 332 Ma isaccepted for the base of the Asbian.Some K/Ar dates are available for vol-canic rocks within the LateCarboniferous (Silesian) sequences ofthe Tamworth Trough. In the absence ofbiostratigraphic evidence, their ages maybe approximately determined from theestimates given on the Hess & Lippolt(1986) scale. For example, the 319 Madate for the Ermelo Dacite Tuff at thebase of the Clifden Formation in theRocky Creek Syncline indicates aNamurian age, and a tuff above thatlevel, dated 313 Ma, is probably earlyWestphalian (Roberts, in McKelvey &McPhie, 1985). Pitchstones from theupper part of the CurrabubulaFormation in the Werrie Syncline haveyielded dates of 302±44 and 295±44 Ma(Roberts, in McPhie, 1984), which wouldplace them respectively within theStephanian and about the Carbon-iferous/Permian boundary. However,until these determinations are re-examined using the SHRIMP ionmicroprobe their reliability remains inquestion.

Late Carboniferous (Silesian) dates are• taken from the work of Hess & Lippolt

(1986), who determined Ar40/Ar39 ageson sanidines taken frombiostratigraphically well datedCarboniferous tonsteins in West

• Germany and Czechoslovakia. The datesare:

303 Ma - Stephanian B/Stephanian Aboundary

• 306 Ma - Westphalian/Stephanianboundary

309 Ma - Westphalian C/Westphalian Bboundary

311 Ma - Westphalian B/Westphalian C• boundary

315 Ma - Westphalian A/Namurianboundary

326 Ma - Visean/Namurian boundary

10 P.J. JONES

•

Jones (1988) compared isotopic age evi-dence and the magnetostratigraphy ofthe Paterson Volcanics, accepting theavailable K/Ar dates with an averageage of 308 Ma, which placed them onthe Hess & Lippolt (1985) scale inWestphalian C. However the conclusionthat the normally magnetized PatersonToscanite, at the base of the Kiamanreversed interval, could be correlatedwith the zone of mixed polarities withinBritish Westphalian C coals (Noltimier& Ellwood, 1977), must now be rejected.New dating of zircon from the PattersonToscanite now indicates a much older(Brigantian) age (Roberts et al., 1991).This and other recent SHRIMP ionmicroprobe work in eastern Australiashows that the magnetostratigraphy forthe Carboniferous as synthesised byPalmer et al. (1985) needs extensiveimprovement before it can be applied tothe solution of stratigraphic problems.

The Carboniferous/Permian boundary,taken as 295 Ma on the charts, was orig-inally arrived at as a compromisebetween the 290 Ma date of De Souza(1982) and Forster & Warrington (1985),and the 300 Ma date of Lippolt & Hess(1985). However recent Ar/Ar resultsreported by Hess & Lippolt (1986)suggest that the actual date may becloser to 300 Ma than previouslythought, but the 295 Ma date is retainedhere for consistency with the Permianchart of Archbold & Dickins (1991).Hess & Lippolt (1986) dated a tuff inStephanian C in Baden Baden which isprobably older than the top of theCarboniferous in the Autun Basin ofFrance (however precise correlationfrom these nonmarine beds to themarine succession in the southern Uralsis still uncertain). The 295 Ma date forthe base of the Permian is still consider-

ably older than the 286 Ma date ofHarland et al. (1982), or the 290 Madate of Harland et al. (1990).

AUSTRALIAN BIOCHRONOLOGY

Roberts (1985a) prepared a comprehen-sive set of correlation charts for theAustralian Carboniferous which incorpor-ated a survey of the biostratigraphicevidence on which the correlations werebased. The present review has drawnsubstantially on his account, but withconsiderable revision to take account ofmore recent work. Most of the papersdealing with Carboniferouspalaeontology published since 1985 havedealt with trilobites, ostracods, fish, andpalynology. Roberts (1985a,b) hasprovided more Australian referencesthan given here, and these works shouldbe consulted for further details of theearly development of AustralianCarboniferous stratigraphy.

Most of the major groups known fromthe Late Palaeozoic fossil record arerepresented in the Carboniferous rocksof Australia, but some are very rare (e.g.insects; Riek, 1973, 1976), and othershave been of limited use in age datingand correlation, although with furtherstudy they may also prove of somebiostratigraphic significance (e.g. Polyzoa- Engel, 1989; plant macrofossils -Gould, 1975; Retallack, 1980; Rigby,1985). Other taxonomic groups whichare better known are briefly summarisedbelow from the point of view ofbiostratigraphic utility, beginning withthose which have been most widelyapplied in biochronological analysis ofthe Australian Carboniferous succession(brachiopods, conodonts, palynofloras;for general zonations based on thesegroups see Chart 1).

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Brachiopods are well-represented in theCarboniferous marine shelf sediments ofAustralia, and are distributed over awide range of lithologies. Markedchanges in faunal composition through

• time have proved the utility of the groupfor biostratigraphic studies andcorrelation in eastern and WesternAustralia. Two zonal schemes based onbrachiopods have been established: one

• for the New England and YarrolOrogens and the Broken RiverEmbayment of eastern Australia(Roberts, 1975); the other for theBonaparte basin of Western Australia

• (Roberts, 1971; Thomas, 1971). Some ofthe zones established for the BonaparteBasin can be identified in other basins inWestern Australia (Canning andCarnarvon Basins), but detailed work is

• needed to determine whether all thezones can be generally appliedthroughout the state. Both brachiopodschemes have been used, together withconodont zones in Western Australia, inthe correlation of the CarboniferousSystem of Australia (Jones et al., 1973).Differences between the composition ofthe brachiopod faunas in eastern andWestern Australia have been explainedeither as two zoogeographic provinces,caused by geographic isolation (Roberts,1971), or environmental factors relatedto the abundance of carbonates in thewest and of volcanogenic clastics in theeast (Runnegar & Campbell, 1976).There is still scope for the investigationof the Carboniferous succession ofbrachiopod faunas, in terms ofcommunity associations andecostratigraphy.

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CARBONIFEROUS 11

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1. Key Groups

Brachiopods (Chart 1, column 15,16;Chart 3, column 5)

The history of biostratigraphic researchon eastern Australian Carboniferousbrachiopod faunas has been summarizedby Roberts (1975, 1985a). The first sys-tematic biostratigraphic work of Maxwell(1954) recognised a zonal sequence ofbrachiopod faunas in the Mt Morgandistrict of Queensland. In New SouthWales, Campbell (1955, 1956, 1957,1961) and Campbell & Engel (1963)studied the taxonomy and succession ofCarboniferous faunas, and Roberts(1965) proposed a partial early zonation,which was later modified by Campbell &Roberts (1969). In Queensland, Driscoll(1960), McKellar (1967), and Dear(1968) proposed local assemblage zones,termed faunas or beds, in isolated partsof the Yanol Orogen. Campbell &McKellar (1969) integrated the datafrom both the Yarrol and New EnglandOrogens into a comprehensive zonalscheme that was applied by-Jones et al.(1973) throughout eastern Australia.However, this zonal scheme still lackeda firm stratigraphic basis because of thelack of detailed geological mapping,necessary to resolve the problems causedby complexity of the structural geology.After detailed geological mapping of thesouthern New England region by Roberts& Oversby (1974), and unpublished workby students of the Universities of NewSouth Wales and Newcastle (supervisedby J. Roberts and B.A. Engelrespectively) the brachiopod zones wereproperly related to the mappedsequences. Roberts (1975) establishedreference sections for the earlyCarboniferous brachiopod zones,together with species range charts, andRoberts et al. (1976) defined referencesections for the middle to lateCarboniferous zones. Other taxonomicand biostratigraphic data have beenprovided by Maxwell (1961a, 1964),Engel (1975, 1980), Runnegar &

12 P.J. JONES

McClung (1975), Roberts (1976), Peou &Engel (1979), and Peou (1979).

The relationship of brachiopod zones toconodont zones in the eastern AustralianCarboniferous sequence has been investi-gated by several researchers. Discrep-ancies between the distribution of con-odont and brachiopod zones within thesame Dinantian sections in easternAustralia have been pointed out byseveral authors (e.g. Roberts, 1975; Jones& Roberts, 1976; Mory & Crane, 1982;Campbell et al., 1983). Such conflictingopinions are more apparent than real,having developed as a result of insuf-ficient data, and misinterpretations of thefossil evidence, in some cases of thebrachiopods, and in others of the cono-donts and anunonoids.

The biostratigraphy of the conodonts isnot in conflict with that of thebrachiopods (cf. Campbell et al., 1983),but serves as a precision tool by whichthe brachiopod zonation may becalibrated against an international scale.It also identifies the weak arguments thatcan be rejected from the otherwise firmevidence on which the brachiopodzonation is based.

The confusion caused bymisinterpretation of the brachiopodevidence, is exemplified by thebiochronologic position of the Tul-cumbella tenuistriata Zone at MountMorgan, Queensland, as based on theconodont evidence reported by Mory &Crane (1982). The source of confusion isthe premise that the Schizophoria Zone(Maxwell, 1954) and Fauna A (McKellar,1967) in Queensland, are equivalent tothe Spinfer so! Zone of New SouthWales, a correlation tacitedly implied byJones et al. (1973), and subsequentlyaccepted in Jones & Roberts (1976), and

Roberts (1975, 1985a). By inference, thiswould mean that the tenuistriata Zonelies stratigraphically below theSchizophoria Zone and Fauna A.Accepting this premise, Mory & Crane(1982) presented the paradox of thetenuistriata Zone, in terms of conodontzonation, lying below the sulcata Zone atMount Morgan, yet lying stratigraphicallyabout 100 m above the sandbergi Zone,near Wirrabilla, NSW. However it hasbeen pointed out that the conodontsfrom the Wirrabilla sequence are not inthe same section as the brachiopods(Campbell et al. 1983).

Mory & Crane (1982) also showed thatthe Schizophoria Zone has a similarstratigraphical range (sulcata to withinthe Lower crenulata Zone). Thus, it nowseems that Mory & Crane's (1982) maincontribution to the brachiopod biostrat-igraphy was by demonstrating i) thelower Tournaisian (and partly Strunian)age for the tenuistriata Zone, and ii) theSchizophoria Zone and Fauna A are bestcorrelated with the tenuistriata Zone, andnot with the so/ Zone.

On Charts 1 and 3 the base of the Tul-cumbella tenuistriata Zone is placed interms of the siphonodellid zonation ofSandberg et al. (1978), below the base ofthe Siphonodella sulcata Zone, that isbelow the Devonian/Carboniferousboundary. The base of the Spinfer so!Zone is placed within the lower part ofthe Lower crenulata Zone for thefollowing reasons. In the Rocky CreekSyncline, early Tournaisian brachiopodsfrom the top of the Tulcumbellatenuistriata Zone occur at the base of thetype section of the Luton Formation(Campbell & McKellar, 1969; Roberts,1975) about 100m stratigraphically abovethe Siphonodella sandbergi Zone (but asnoted above not in the same section).

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Therefore the tenuistriata Zone at thebase of the type section of the LutonFormation is probably equivalent to thebasal part of the Lower crenulata Zone.Because the so! Zone in the RangariLimestone Member of the TulcumbaSandstone also belongs to the Lowercrenulata Zone (Mory & Crane, 1982), itappears reasonable to conclude that thetenuistriata Zone in the Tulcumba Sand-stone in the Swain's Gully section of theWerrie Syncline is also equivalent to thebasal Lower crenulata Zone, and can beassumed to be the youngest knownoccurrence of the tenuistriata zone.

Conodonts (Chart 1, column 12; Chart 2;Chart 3, column 4)

graphic significance of these faunas wasreported by Jones & Druce (1966), andtaxonomic documentation was laterprovided by Druce (1969). Subsequentstudies on Lower Carboniferousconodont faunas were concentrated inWestern Australia (e.g. Nicoll & Drtice,1979), but with small faunas describedfrom eastern Australia (Druce, 1970;Jenkins, 1974; Webb, 1977; Pickett, 1981;Mory & Crane, 1982). Recently Jenkinset al. (in press) have presented a newzonation for the Visean based onextensive taxonomic descriptions. Earliersummaries and review compilations havebeen provided by Jones et al. (1973),Druce (1974), Jones & Roberts (1976),and Nicoll & Jenkins (1985).

Apart from the descriptions of smallfaunas from Queensland (Druce, 1970;Webb, 1977; Pickett, 1981), the firstsignificant work on Carboniferous cono-dont faunas from eastern Australia wasthe conodont zonation proposed byJenkins (1974) for New South Wales.Jenkins (1974) summarised a successionof seven conodont faunas, and proposedsix informal biostratigraphic zones abovethe lowest fauna, which wascharacterised by Siphonodella.Subsequently Mory & Crane (1982)developed a siphonodellid zonationwhich could be tied into internationalschemes (e.g. Sandberg et al. 1978).

Zonations based on Siphonodella havealso been recognised in WesternAustralia (Druce, 1969; Nicoll & Druce,1979), but siphonodellids appear to bepoorly represented compared to thosefrom eastern Australia. However recentwork by Macquarie University in theCanning Basin has demonstrated a bettersiphonodellid representation across theDevonian-Carboniferous boundary.

The base of the Schellwienella cf. burling-tonensis Zone is placed at the base of theGnathodus punctatus Zone of Jenkins(1974) which is its lowest known occur-

• rence (Roberts, et al., in press). Schell-wienella cf. burlingtonensis itself is alsofound in the G. semiglaber Zone in theCarellan section (Jones, in Campbell etal. 1983), and elsewhere.^In the

• Gresford section it is associated withanchoralis Zone conodonts, which givesthe upper limit to this zone (Chart 3,columns 4,5).

• Visean brachiopod zones from Orthotetesaustralis to M. barringtonensis have beencalibrated by integrating the new Viseanconodont zonation of Jenkins et al. (inpress), tied in with selected levels in theforam zonation of Mamet (Chart 3,column 3).^These correlations areexplained in detail in Roberts et al. (inpress).

Carboniferous conodonts were first men-tioned by McWhae et al. (1958) andGlenister (1960) from the Bonaparte

• Basin, Western Australia. The biostrati-

14 P.J. JONESItIn terms of the Belgium Dinantian

sequence, the Gnathodus punctatus Zoneof Jenkins (1974) is correlated here withthe uppermost siphonodellid zone(Gnathodus punctatus [Cc 11] Zone), atthe top of the Hastarian Stage (Tn2c),following the scheme of Paproth et al.(1983, table 2). This differs from figure 7of Mory & Crane (1982), who correlatethe G. punctatus Zone (of Jenkins, 1974)with the base of the Polygnathuscommunis carina Zone at the base of theIvorian Stage (Tn3a). This change isconsistent with the data provided byseveral authors (e.g., Chauff, 1983;Carman, 1987) on the upper part of therange of Gnathodus punctatus.

Thus, in these charts, the base of theGnathodus semiglaber Zone of Jenkins(1974), is taken as the base of theIvorian (Tn3), the upper Tournaisian ofBelgium (Chart 1). In terms of standardconodont zonations (see Chart 2), thishorizon corresponds to the base of theLower typicus Zone of Lane et al. (1980),and to the base of the cuneiformis Zoneof Belka & Groessens (1986).

The recent research of Jenkins et al. (inpress) concerns the conodont sequenceof the Visean rocks above theScaliognathus anchoralis Zone in theNew England Orogen, New South Wales,and the Yarrol Orogen, Queensland, andDr T.B.H. Jenkins has kindly permittedme to use some of the results of thisresearch, prior to its publication (zones1-4 on each chart). For reasons ofpublication priority new names of cono-dont taxa, and biozones, are temporarilyomitted from the scheme presented here.Definitions of the Visean biozones foreastern Australia are provided by Jenkinset al. (in press), and here I give only theminimum data necessary for theintegration of the conodont scale with

the scales based on other marineinvertebrate fossil groups.

The four conodont biozones above theScaliognathus anchoralis Zone are num-bered in ascending order. The lowestbiozone (Zone 1) replaces the fourpreviously proposed for the early Visean(V1) of eastern Australia viz., thePseudopolygnathus cf. nodorrzatginatusZone and the Patrognathus? cf.capricornis Zone of Jenkins (1974), andthe undefined Gnathodus sp. nov. Zoneand the Polygnathus bischoffi Zone ofMory (1982).

Taxa from the base of Zone 1 that firstappear in the top of the Scaliognathusanchoralis Zone include Gnathodus sp. Bof Jenkins (1974), and key species suchas Polygnathus bischoffi and Gnathodussubbilineatus that indicate an earlyVisean age.

The base of Zone 2 is placed within thelower (VIb) part of the Arundian.Important taxa include new species ofAdetognathus. Difficulties in determiningprecise correlations at this level becauseof the endemic nature of the Australianconodont faunas are discussed in detailby Jenkins et al. (in press).

The base of Zone 3 is considered toapproximate to the base of theHolkerian. Important taxa in this zoneinclude the first appearance ofGnathodus girtyi, Lochriea commutata,and new species belonging toAdetognathus and Mestognathus.

The base of Zone 4 is characterised byGnathodus bilineatus (Roundy), and G.texanus Roundy (sensu stricto, as revisedby Jenkins et al., in press). The firstentry of bilineatus in western Europeestablishes an early Asbian age for this

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CARBONIFEROUS 15• level. The top of this zone containsRhachistognathus prolbacs Baesemann &Lane 1985, which first appears in thenaviculus Zone, that is the equivalent ofthe Chokerian (E2) stage of Britain.Present evidence indicates that this is theoldest record of R. prolixus, and on thisbasis Zone 4 is extended into the earlyNamurian.

• The youngest known conodonts in theCarboniferous of Australia weredescribed by Palmieri (1969) fromsoutheastern Queensland (for comments,see Jones et al., 1973; Druce 1974;

• Lane & Straka, 1974; Jones & Roberts,1976, and Nicoll & Jenkins, 1985).Palmieri's samples contained poorlypreserved faunas, possibly of differentages, ranging from early Namurian to

• early Westphalian.

Mollusca (Ammonoids) (Chart 3)

Almost all the occurrences ofCarboniferous ammonoids in Australiahave been reported from the easternstates (for a brief history of studies onthis group see Delepine, 1941; Campbellet al., 1983; Campbell in Roberts,1985a). The only Carboniferousammonoids known from WesternAustralia were found in the LaurelFormation, on the Lennard Shelf,Canning Basin. They were referred byGlenister (1960) to a single species ofImitoceras.

(modified after Ramsbottom & Sanders,1984, and Riley, 1990) is shown incolumn 2 of the Chart for comparison.

The oldest eastern Australianammonoids [Protocanites planorbiformis(Etheridge) and Pseudarietitesammonitiformis (Etheridge)] were firstrecorded from an unknown locality inthe Rockhampton district, Queensland(Jack & Etheridge, 1892; Whitehouse,1930). They were later shown to havecome from the mudstone overlying theGudman Oolite at the base of the Ma-lchi Formation (Fleming, 1967), andwere associated with brachiopods of thesame age as those of the SchizophoriaZone at Mount Morgan (McKellar,1967). The ammonoid fauna may be ofCu I age ( =Gattendorfia Zone) or a littleyounger. As the conodonts from theGudman Oolite belong to the Lowercrenulata Zone (Mory & Crane, 1982)the ammonoids are probably of earlyTn2a age, and are the earliestrepresentatives in the so/ Zone(Campbell et al., 1983).

Two other ammonoid faunas are presenthigher in the so! Zone in the northernpart of the Tamworth Trough, NSW. Inthe Bellevue Syncline, Protocanites careyiand P. australis near the base of theNamoi Formation at Rangari (localityL76 of Campbell & Engel, 1963), arereferrable to the isosticha-Uppercrenulata conodont zone of Mory &Crane, 1982; Mory, 1983). Thesearnmonoid species are accompanied byMuensteroceras merlewoodense andImitoceras weniense in the upper part ofthe Namoi Formation at Rangari(locality L77 of Campbell & Engel,1963), at the top of the so/ Zone. At asimilar level in the Namoi Formation inthe Werrie Syncline, Protocanitesaustralis, P. careyi and Muensteroceras

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In eastern Australia, ammonoids havebeen reported from at least 17 differentstratigraphic horizons. In Chart 3 the

• stratigraphic distribution of all namedAustralian species from the EarlyCarboniferous (Dinantian) are plottedagainst the east Australian brachiopodscale as calibrated by the latest conodont

• zonation. A European goniatite zonation

16 P.J. JONES •delepinei occur in the original localitydescribed by Delepine (1941) in theSwains Gully section (locality L22 ofCampbell & Engel, 1963). These am-monoid faunas are also referred to theisosticha-Up per crenulata conodont zoneof Mory & Crane (1982).

A slightly younger ammonoid fauna con-sisting of Muensteroceras jenkinsi, Irinoc-eras sp. and Ammonellipsites (Amrnonel-lipsites) sp. occurs in the burlingtonensisZone at the top of the DangarfieldFormation. This fauna lies within theGnathodus punctatus conodont zone ofJenkins (1974), and would be middleToumaisian (Tn2c) in age.

Other ammonoid taxa (Karagandocerassp. and Protocanites sp.) are known fromwhat is regarded as the lowest part ofthe burlingtonensis Zone at the top of theLuton Formation (Campbell et al., 1983).These species-can also be referred to theGnathodus punctatus conodont zone ofJenldns (1974).

A younger ammonoid fauna consisting ofMuensteroceras delepinei, Protocanitescareyi and P. australis is present in theCarellan limestone sequence in theNamoi Formation (Campbell et al.,1983) within the lower half of theGnathodus sp. A Zone of Jenkins (1974).Although the associated brachiopods inthe Carellan limestone are not definitiveof either the so/ or the burlingtonensisZones, the nominate species of the latterzone has been found in the Gnathodussemiglaber Zone of Jenkins (1974), belowthe ammonoids (Jones in Campbell etal., 1983: 76).

A higher ammonoid fauna occurs in theupper part of the Namoi Formation inthe Swain's Gully section in the WerrieSyncline. It consists of an association of

Protocanites cf. careyi, both below andabove Amrnonellipsites sp.

The incoming of Erdbachites sp. A in theupper part of the Schellwienella cf.burlingtonensis Zone near the top of theGoonoo Goonoo Mudstone on theeastern limb of the Werrie Syncline wasconsidered to be the first indication of aVisean age (Campbell et al., 1983:79).This species was compared with E.djaprakensis (Librovich), a member ofthe basal Visean kochi Zone fauna (butsee Riley, in press). On Chart 3 thisspecies is now considered to probably liewithin the anchoralis Zone, of lateToumaisian age.

An ammonoid fauna occurs in the Bon-nington Siltstone, which containsbrachiopods of the Orthotetes australisZone. Brown et al. (1965) describedBeyrichoceras trevallynense andProlecanites sp. (but these determinationsare challenged by Riley, 1990a, 1991),and conodont evidence places this faunain the Visean (late Chadian-earlyArundian), in the middle part of zone 1of Jenkins et al. (in press).

A fauna in the Flagstaff Formation (incl-uding Erdbachites sp. B) is lower thanCantabricanites jelli (Roberts et al., inpress; cf. Campbell et al., 1983). Thelatter species (with Irinoceras tuba)occurs in the elegans subzone of theaspinosa Zone, ranging up into thefortimuscula Zone.

The most diverse ammonoid faunasoccur in the fortimuscula Zone ofQueensland, in the MundubberaSandstone (Corsers Bridge Member) andDakiel Formations, where at least 11species are recorded (listed in column 6of Chart 3). In contrast, the fortimusculaZone in NSW contains a much poorer

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Although the first ostracod speciesdescribed from Australia was Carbonifer-ous (Morris, in Strzelecki, 1845)

• ostracods of this age were virtuallyneglected in this continent for more thana century. These microfossils, of provenbiostratigraphic value in exploration forfossil fuels in the Carboniferous of North

• America, western Europe, USSR, andChina, were not used for this purpose inAustralia until the late 1950's, when thefirst evaluations of the biostratigraphicuse of this group were carried out to

• provide correlations for Carboniferousand Late Devonian rocks encountered inpetroleum exploration wells in theCanning and Bonaparte Basins, WesternAustralia (Jones, 1958, 1959, 1961, 1962a,b,c). So far the taxonomic descriptionof these extensive assemblages is limitedto some eridostracans (Jones, 1962c,1968), and a formal taxonomicdocumentation of Carboniferousostracods from the Bonaparte Basin(Jones, 1989).

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fauna (`Girtyoceras' sp.; Campbell &McKelvey, 1972). The youngestDinantian ammonoid in the Australianrecord is 'Beyrichoceras' bootibootiensis inthe barringtonensis Zone at the base ofthe Yagon Siltstone (Campbell et al.,1983).

Finally, the youngest knownCarboniferous ammonoid in Australia,Cravenoceras kullatinense occurs in thelower part of the Levipustula levis Zonein the Kullatine Formation of theKempsey district, NSW.

Ostracoda (Chart 1, column 17)

using these groups, and cognate and con-specific ostracod species. The descriptionby Jones (1989) of Ostracoda from theEarly Carboniferous of the BonaparteBasin provides a biostratigraphic scale ofeight assemblages, based on the distribu-tion of 29 beyrichicopid and kirkbyocopespecies. Other components of theostracod fauna (Platycopa, Metacopa,Parapodocopa and Paraparchiticopa) arebeing studied to enhance thebiochronological value of the ostracodtime-scale. To date, the older threeassemblages, of early and middleTournaisian age, have also beenrecognized in the Laurel Formation ofthe Canning Basin.

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•The ostracod scale given on Chart 1 isinternally controlled by conodont andforaminiferid zonations, and is also cali-brated against the Dinantian time-scale

Plant microfossils (Chart 1, column 18)

Since Carboniferous plant microfossilswere first reported from Australia(Balme, 1960), they have proven to bewidely distributed, and of considerablestratigraphic value. Key referencesinclude Playford & Helby (1968),Playford (1971, 1972, 1976), Kemp et al.(1977), Powis (1979), and Truswell(1980). Balme (1980) discussedpalynological evidence bearing on theCarboniferous-Permian boundaryproblem in Gondwana sequences, andPlayford (1985) review Early Carbonifer-ous palynomorphs from Australia. Viseanspores from the Bonaparte Basin havebeen described by Playford &Satterthwait (1985, 1986, 1988). Thesummary zonation (Chart 1, column 18)is a composite attempting to integratewestern and eastern Australiansequences. More confidence is placed inthe lower part of the column, which isfounded on the detailed taxonomic workof G. Playford from the Bonaparte andCanning Basins in Western Australia.However these zones are also identifiedin the east, for example in the

18 P.J. JONES

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Drummond Basin (Playford, 1977, 1978).The post-maculosa part of the zonationfollows recent work by Jones & Truswell(in press) in the Galilee Basin.

Playford (1986) has published the onlyaccount, to date, of megaspores from theAustralian Carboniferous. He reportedthat they are rarely encountered andfragmentary in the Carboniferous ofAustralia, mostly in marine sequencesexamined for miospores and pollen. Atpresent, megaspores are not importantfor biostratigraphic studies in theAustralian Carboniferous, but increasedknowledge of these larger palynomorphscould be of palaeobotanical, if notstratigraphical significance.

2. Other Groups

Conchostraca

The Conchostraca are fresh-water-adapted crustaceans with a smallchitinophosphatic bivalved shell. Like theOstracoda, they are potentially goodlocal biostratigraphic and palaeoecologicindicators. To date, only twoconchostracan faunas are known fromthe Carboniferous of Australia, bothwithin the Lower Carboniferous. Thepossibly older of the two consists of asingle species Leaia (Hemicycloleaia)drummondensis, and is present in theRaymond Formation (?late Tournaisian- early Visean) of the Drummond Basin,Queensland (Tasch, 1979). The secondfauna is more diverse, consisting of fivegenera - Monoleaia, Leaia, Rostroleaia,Limnadiopsileaia, and Cyzicus. Thisfauna is so far recorded only in thesubsurface Anderson Formation (Visean)in the Canning Basin, Western Australia(Tasch & Jones, 1979). An olderocurrence of leaiid conchostracans [Leaia(Hemicycloleaia), and Rostroleaia] in the

Middle Devonian of South China (Shen,1978) suggests a probable source forthose Lower Carboniferous taxa in theCanning Basin (Tasch, 1987).

Corals

Although the corals have beenintensively studied in the Carboniferousof Australia, in general they have a morelimited geographic and stratigraphicdistribution than brachiopods (Campbell& McKellar, 1969), and as yet no coralbiozonation has been established. Thegroup has been used for localcorrelation, but seldom has it been usedfor intercontinental correlation, and thenonly in general terms. Pickett & WuWang-shi (1990) have recently reviewedthe biostratigraphic potential of theCarboniferous coral faunas of easternAustralia. Webb (1989, 1990) hasrecently studied the systematics,biostratigraphy, and palaeoecology ofLower Carboniferous coral faunas in thenorthern Yarrol Basin.

Foraminiferida and Algae

The first authentic Carboniferous foram-iniferids from Australia were reported bythe present author (Jones, 1958) fromthe Bonaparte Basin. Subsequentdescriptions included Belford (1968,1970) and Mamet & Belford (1968) onmaterial from the Bonaparte Basin, andMamet & Playford (1968) on materialfrom the Canning Basin. Works onCarboniferous algae from the west arelimited to Veevers (1970), and Mamet &Roux (1983) on material from theBonaparte Basin.

No zonations based on foraminiferidsand algae have been proposed for theAustralian Carboniferous. However, theirbiostratigraphic potential is shown by a

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few taxonomic studies which havepermitted assignment to the globalzonations established by Mamet (1974).The study of Australian Carboniferousalgae by Mamet & Roux (1983) wasmainly taxonomic, with no emphasis onthe biostratigraphy. The results of thiswork need to be put into abiostratigraphic context, but this has notbeen attempted here.

In the volcanogenic provinces of easternAustralia there are few recorded occur-rences of forams and algae, but wherepresent they have proved biostratigraphi-

• cally useful. For example forams andalgae identified by B.L. Mamet (in Rob-erts, 1975) from the same limestonesnear the top of the Delepinea aspinosaZone (Linoprotonia tenuirugosus

• Subzone) at Brownmore (section 85)sampled by Jenkins (1974) are fromMamet's zones 13 to 15 ((V2b--V3b).Those identified by Mamet (in Roberts,1975) from limestones in the lower part

• of the aspinosa Zone (Inflatia elegansSubzone) at Rouchel Brook (Roberts &Oversby, 1974) are from Mamet's zones11 to 12 (Vlb--V2a) or perhaps younger.

Mamet's global foraminiferid zonation isgiven on Chart 1, column 9 (zones 3-23).Above this is shown Wilde's (1984) fusul-inid zonation for the latestCarboniferous-earliest Permian sequenceNorth America and the Soviet Union.For the Dinantian Mamet's zones 6-16sare given on Chart 3, column 3. Thisprovides a framework for dating selectedintervals where foraminifera and algaehave been recorded (e.g. Roberts &Oversby, 1974).

Mollusca (Bivalvia, Gastropoda)

Most descriptions of bivalve and• gastropod molluscs have been presented

within works describing other marineinvertebrate groups, as part of the entireshelly fauna (e.g. Etheridge 1890a,b,1896, 1898, 1907; de Koninck 1877;Benson 1921; Campbell 1961, 1962;Roberts 1963; Campbell & Engel 1963;and Campbell & McKelvey 1971).However studies solely concerned withthese Carboniferous molluscs includethose on gastropods by Maxwell (1961b)and more recently by Yoo (1988). As yetthese groups have not been analysed toprovide detailed biostratigraphicinformation.

Radiolaria

Despite the recognition of radiolarians inPalaeozoic rocks from the New EnglandFold Belt last century (David & Pittman,1899) and the detailed description of awell-preserved and varied MiddleDevonian fauna (Hinde, 1899), Carbonif-erous Radiolaria have been reported inmainly bedded cherts from this regiononly recently (Aitchison, 1988a-d; Ishigaet al., 1988). No Carboniferousradiolarians have been recorded fromelsewhere in eastern Australia, and theyhave yet to be reported from WesternAustralia. Thus, the study of thebiostratigraphy of CarboniferousRadiolaria in Australia is in its pion-eering stage.

Results so far demonstrate the potentialof radiolarian studies for age determinat-ion, and the subsequent deciphering ofthe complex geological history of theNew England Fold Belt (Aitchison, 1989;Aitchison & Flood, 1990).

Trilobites

Only one trilobite superfamily (theProetacea) survived into theCarboniferous, but 'there is a far greater

20 P.J. JONES •abundance and diversity of forms than isusually realized, and in parts of theCarboniferous System trilobites can be asimportant as many other fossil groups'(Owens, 1990: 96). This has been borneout by recent trilobite studies in Europe(e.g. Hahn & Hahn, 1988; Osmolska,1970; Thomas, Owens, & Rushton, 1984,Owens, 1986), and in eastern Australia(Engel & Morris, 1975, 1980, 1983, 1984,1985, 1989, 1991).

For the Australian Carboniferous,species ranges for various genera havebeen documented (e.g. Engel & Morris,1985, table 2; in press, tables 1-5), andthe systematic work of these authors hasprovided a sound taxonomic basis onwhich to formalise a biostratigraphicscheme, although as yet no completetrilobite zonation has been put together.

Vertebrates

Fish faunas are not as well known in theCarboniferous as they are in theDevonian of Australia, and consequentlythey have not received the samebiostratigraphic attention. However,some important recent studies ofCarboniferous fish faunas from Victoriaand Queensland may provide thetaxonomic basis for more detailedbiostratigraphic analysis. In Victoria, thewell• known Lower Carboniferous(Toumaisian) Mansfield fauna (SmithWoodward 1906; Hills, 1958) hasrecently been redescribed by Long(1988), and the fish remains of theGrampians in western Victoria (Chap-man, 1917) of supposed Carboniferousage, have been shown to be Devonian(Turner, 1986). In Queensland, a richrhipidistian, palaeoniscid andacanthodian fish fauna is under studyfrom the Raymond Formation in theDrummond Basin. The palaeoniscidsfrom this and other faunas may provide

an interesting comparison with the faunaof similar age described by Gardiner(1969) from the Waaipoort Formation, atthe top of the Witteberg Group, CapeProvince, South Africa. EarlyCarboniferous shark remains have beendescribed by Turner (1982) from NSW,and reported by Turner (1990) from theRockhampton district in Queensland.These may be compared with thosepreviously reported by Thomas (1959)from the Lower Carboniferous (Tou-maisian) Laurel Formation in theCanning Basin of Western Australia.

ACKNOWLEDGEMENTS

Many colleagues have contributed workand discussion, the results of which havebeen included in the charts and notes. Iespecially thank Dr Huw Jenkins (Unive-rsity of Sydney) for providing me withthe abstract and copies of the figuresfrom his work in press with Dr DavidCrane and Dr Arthur Mory on conodontbiostratigraphy of the Visean Series ineastern Australia, and allowing me to usethe results of this research in thesecharts. Professor John Roberts(University of NSW) freely discussed theresults of his brachiopod research, DrBrian Engel (University of Newcastle)provided me with the results of his jointstudy with Dr Noreen Morris on theCarboniferous trilobite faunas of easternAustralia, and Dr J.M. Dickins and DrClinton Foster (BMR) made manyhelpful comments on earlier versions ofthe charts. I thank Dr Gavin C. Young(BMR) for his advice, support andencouragement in steering this firstversion of the Carboniferous chartthrough to completion, and Peter Brown(BMR) for drafting the charts andhandling the many amendments andadditions. The final edit was done byLesley Jones.

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CARBONIFEROUS 37•

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Bonaparte Gulf Basin, northwesternAustralia. Bureau of Mineral Resources,Australia, Bulletin 122.

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38 P.J. JONES

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CARBONIFEROUS 39• THOMAS, A.T., OWENS, R.M., &RUSHTON, A.W.A., 1984 - Trilobites inBritish Stratigraphy. Special Report ofthe Geological Society of London, 16, 1-78.• THOMAS, G.A., 1957 - LowerCarboniferous deposits in the FitzroyBasin, Western Australia. AustralianJournal of Science 19, 160-1.

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42 P.J. JONES

CAPTIONS FOR CHARTS 1-3

CHART 1. Correlations between the geochronologic and biochronologic scales ofAustralia and those of western Europe, Soviet Union, USA, South China and Argentina.Column 1: Preferred dates are shown against those of Harland et al. (1990);Column 2: Composite subdivision of succession in Belgium, British Isles, France andGermany, after Conil et al. (1976), George et al. (1976), Ramsbottom et al. (1978),Paproth et al. (1983), Owens et al. (1985), Riley et al. (1985), Bouroz & Doubinger(1977), Doubinger & Bouroz (1984), and Wagner & Prins (1985);Columns 3,4: Unified USSR scales for the eastern European platform and the UralMountains, after Rotai (1979), Solovieva (1985), Solovieva et al. (1985a,b), Vdovenko etal. (1987), Yabolkov (1975), and Vissarionova (1975).Columns 5,6: Reference sections for the USA, after Weller et al. (1948), Moore et al.(1944) Maples & Waters (1987), Shaver (1984), Sutherland & Manger (1984), Wilde(1975, 1984), and Clendening (1975).Column 7: Ammonoid genozones, after Ramsbottom & Saunders (1984), and Riley (1990,1991).Column 8: Foraminiferid zonations of the Soviet Union, after Rotai (1979), Lipina &Reitlinger (1970), Lipina & Tschigova (1975), Vdovenko et al. (1987), and Davydov(1988).Column 9: Zones 3-23 of Mamet's global foraminiferid zonation (Mamet, 1974) andWilde's (1984) fusulinid zonation for the latest Carboniferous-earliest Permian sequenceNorth America and the Soviet Union.Column 10: Foraminiferal zonation for USA after Wilde (1975, 1984), Mamet (1974),Baxter & Brenckle (1982), and Brenckle & Groves (1986).Column 11: Composite conodont zonation after Sandberg et al. (1978), Lane et al. (1911,1980), Higgins (1975, 1981), Lane (1974), Merrill (1975), Movshovich et al. (1979),Chernykh & Reshetkova (1987), and Wang (1991).Column 12: Megafloral zonation after Wagner (1984) and Wagner & Winkler-Prins(1985).Column 13: Microfloral zonation after Owens (1984) and Peppers (1984).Column 14: Conodont zonation for eastern Australia, after Jenkins (1974), Mory & Crane(1982), and Jenkins et al. (in press).Column 15: Brachiopod zonation for eastern Australia, after Roberts (1975) and RobertsCrane & Hunt (1976).Column 16: Brachiopod zonation for western Australia, after Roberts (1971), and Jones(1989).Column 17: Ostracod zonation for Western Australia (Bonaparte Basin), after Jones(1974, 1989).Column 18: Composite microfloral zonation for Australia, after Playford (1971, 1976),Kemp et al. (1977), Foster & Waterhouse (1988), and Jones & Truswell (in press).Columns 19-21: Marine invertebrate, megafloral and microfloral zonations fromArgentina, after Gonzalez (1985, 1989), Taboada (1989), and Archangelsky (1980).Column 22: Stratigraphic subdivision for the Carboniferous of South China (Hunan andGuizhou Provinces), after Zhang (1987) and Wang (1987), with the mid-Aikuanian Eventafter Ji Qiang (1987).

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CARBONIFEROUS 43

• CHART 2. Proposed correlation of Early Carboniferous conodont zonations fromWestern Europe, after Paproth et al. (1983), Voges (1960), Ziegler (1969), Meischner(1970), Sandberg et al. (1978), Lane et al. (1980), Metcalfe (1981), and Varker &Sevastopulo (1985); Australia, after Druce (1969), Nicoll & Druce (1979), Nicoll & Jones(1981), Jones (1989), Jenkins (1974), Mory & Crane (1982) and Jenkins et al. (in press),

• and North America after Collinson et al. (1962, 1971), Thompson (1967), Thompson &Fellows (1970), and Baxter & von Bitter (1984).

CHART 3. Distribution of named Early Carboniferous ammonoid species (column 6),after Campbell et al. (1983), plotted against the Australian brachiopod zonation of

• Roberts (1975) (column 5), as recalibrated by the most recent conodont zonation foreastern Australia (after Jenkins, 1974; Mory & Crane, 1982; Jenkins et al. in press) andthe foram zonation of Mamet (1974). Columns 1, 2 summarise the Early Carboniferousammonoid scale (after Ramsbottom & Saunders, 1984, and Riley, 1990, 1991), and acomposite subdivision for western Europe (after Conil et al., 1976, George et al., 1976,

• and Paproth et al., 1983).

W EST E R 'N E U R 0 P E V? UJ~-----------------'-------------'~~~~07rr----------------------W (!) BELGIUM GERMANY GP~·MAN-U,~·P>RITAIN & IRELAND ~ <{' L.OhlaINATION

w In Paproth efal. I,as VoSes, 1,60; Zicgl ... ,1~9 Sandb.'S.fa/.,I,78; M.teolk, 1,81 Vark"" and (,f) Meischn .. r,1970 L,on" JtI/., 1980 Sev .. sfopulo, 1~85

Gn.IlIootIus Gna;~ 9irlyi

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,..... " 1/1 /IV Gnafhot:lus hilinealus J: ~ bih'MoM Gnedltodus

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""'2 "l: bulfyncki cf.' . ". > -!'N~ ~.~ f' - Z .I0'?Y'P0S,'ICUS C! I': ~ A Eofo,t>hrus cf 'J'P'CUS I _________ -+ ____________ __

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c( G a::'I' hO$$i ~ G. delicafus h7P/lisfriol",s I.LI

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b ,8 Sipl","odel/a U K ;2 ITn 2 i50sfkha

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..:{ P. mornalps Slphonode//a

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4: f..- ~ - ~I 'I~ --?- - -1-----------1 :r -1: "" !l Sf,chModella - Ps. . II .

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Stphonodt://o fX/ Lo d. /: f. m Yorit:!fb v's splcafus frjL du~ Gn.k_;.w//-?,s.,*"f/. w~r UpICa.~ /z -Ilnl[l /fme.hF8 • $~/colD 8.' ,

ko~,/i S. sU!ce1h# 'spt:Trhus U. Pn:1fog/1"fhoq",~ aculeohts?

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A U ST R A L I

&ONAPARTE &ASIN CANNING &ASIN Nicoll." .. Nicoll ~nd Druce, 197'

D,uce,I16' Jo .... ,I,.1 Revised this paper Jonas , I,.,

UNZONED UNZONED INTERVAL INTERVAL

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~ Gnafltodus COvv,!!!",,#tvs

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« ~ ~ 1, C)

~ ~~ - i\il

...J ~" ...J

- ~ ~ ;;; ~~

1i ~ ~~ ~~

?- r--- ?-'-?-

? 7

?

~ i&noobI17Q'Y,i:tmts ~",..{"sn-i"""" 8ispafhodus III ...J Spgfho,YI1Qfhodlls spinu!icoslalu.s U) :::> cosio/us 8isfJ"'fhodus ~ Spafhognalhodu.s t act/lea/us w S,oalk:ynoif70dv$

cann/ngensis

'" fridt:hm!us z 0 ... .., ;:::

"'''' « ZIIl

~ Clycl~I1dlhUS ::;: nodosus e<:

z 0

0 U.

;:: Clyd"'3ndfhu$ "" CPvl/sirormis >Ii SiphO'1oc1ell" " App0I'"'OIh.ol$ A 0 ruadruplicQ'fo-... '" S(.ohOl1odel/a

'" Z coopen

'" ...J

oe S. isosficha- W

p. il1ornoros " ::> il'1orl1ofus fbly!lndfhus I- '" " S. $u/cc:tI·t::t - siphonoa'e/Iv.s ...J

::> CO Po 'porQpefus

Sp«fhD,9m>fkx:lJlS 8is,Pt?fhvs Clyd~"dfhus

~ 1- plumu/us aCtl/~afu$ gJlwernensis

p/umufus ~~

A

N.S.w. & QUEENSLAND Jenkins, 1974 Mor~ GlIna Cra,ne • 1982 J~n in. ef",l,(in prep)

I

I I I !

4

:1E LL n<:

'" l-III

'" :t 2 :t 3 U

z 0 j: « ;:;; P4frognofhvs ? "---I

"" 9 .0 cf. capricornis

1"-

2 LL "-« f-OJ)

<!J f-?- ---'?-- ,----I « ...J

"-

--;-II)

S iii z 0

1 f-<!J z Z z 0

..!!L z

1-2 .(f-

"'" «::IE "oe ~~""thus ",0 f .. cf.notImng,.QifT(7lus

a~ e anchoro/J"s ~~ ~i ~(i!

'" d Gnafhoclus

~ spA u.

Gnafhodu.s - C 0 sem(gktber ::;

'" Z b Grrafhodus

pUr/dolus

- I isosf;cha-

~ Upper cn:nvlafa

"' III

"" cO :;;; ::> u Lower crenulato ...J

'" C! f-

f..-sancl6ergi

~ f-------U)

0 ::> :::E duplicorc:; -------"" 3 0 0 su/co/-o Z

'" ;:;;

CARBONIFEROUS CHART 2

NORTH AMERICA

UPPER MISSISSIPPI VALLEY MISSOURI CANADA

Collin$on,Scottand Rexroad,1962 Thompson, 1~"7 5axhzr And von BiHw; J~84 Collin.on,Re.rOQd.ndThomp .. n,I~71 Thompson.ndF.llowa),70

~~I Gl1crfhodus

t hilineofus -Cavu:1.gnafhus

BEECH CREEK allus

YPRESS (undivided)

I GtTafhodu6 bilineofus -Covllsg/'fofhu~

c/tarocrus 5TE. ~IEY£

IlJ Z 0 l-til Ap«rog",,,fhus Ap,,';o!!nafhu$ IlJ ::;: scalenus - sca/~"us -:::; CavusgHaHtus UNZONED Cavusgnafhus

INTERVAL

III -::J o M ...J

~

...: '" Taphro!Jnt::rfhus

~ Spolho.9l1alftot:Jl yarions -r-- Apofo!!"ulhus ~ coolescens I ~ Subzone ?;;:E ~ <CtoJ ~ (/)...J ~ Ol", i ~111

~

I

~ 'i ~ ~

:i. Gnathodus Gnofl1odus ~ COvuV;Ofhvs ::J TelfOnUS - /'elfonvs - ~ Su zone , :i. Ta,Phroynolhvs 7Rphr~tTafh"s (l 0 UJ , >l

I I

I

? ! G/7O'flrodus Ca-vusgnalhus -bulbasvs Eofaphrvs Intwton~

~ Eol-uphrvs Z 8ddrqgl7afhu$ ':1: Subzone 0 Eofpphrus - dJslor/ps - '" ~ I- ~ ~ ... BClcfr'?!1nafhus Gnafhodus <::~ z Ctlneirorm/s H Lower-~

'<'l~ SubzoMe '" ::> cO

r-zz Bacfrognafhus - f3acfrognafhus -o<w P. cf7mmunis Bacfr0.!1/'TafhllS - P. communis W..J u.(,!) ?s~dopo!yg""'fhH"

mulf/slrialus Z

G. sem&!aber -{il7ofhodu.s

W serniglaber -"- t"%'. mu/fislrii::7/us "- G. sem!gla6er - Po!ygnofhus

'" coml"l7wn/s carina :::E ? communis corina

? I Gnp/ftodw5 .~ ~ punek/us .~ Siphonode//a ~~ coope!ri hassi-

::> ~ u Gnaf-hodus

'" $. isosficha - a-§ Siphonoclel/a W s. coop~ri (l«" puncfaws f- cooperihossi ::> V:i\!:i 0 :c u

-?- ' " SiPh"nrxle//o ~ h·t ctMptrri a:IOjOt!'ri ~ 'l- •

U Siphonode/la ~ag. Siphohode//a

ruadrup/,cc:tft::t ~o; u fJuodrvplicara Siphonode/la -

Pseudopoly!lnofhus ...J S /ob"",,-« s. crenu/a/-a ., - 1-------Z

Siphonoclella S. sandbt!"ryi-

Z M S. dup/ic(7h'~ S. sand h~rg/ -<C dtlJ7licafa :r: S. dvpl/coh::¥

L 7 ?

~ S. suka/a

----lOOiSlANl

LST. U. $.praesu/ca/a DEVONIAN

Comp!!ed IJJO by PJJones, 8M/( Drawn by P J. Brown, 15MR

/ en w ~ W en

~ CS a..

-...J

Z <{

IX: W ~ V'> W

XI U,

I

Z 4: -U W

::!: <{

IX: W

~

Z

<i

W

<9

<.(

if)

0

Z « -~

0 0 I ct. W 0 Z -:::.c

::J

;.

\ i,\ ~~ ," "'i .'

t· "

.)

c ,'2- ,.

~ (j'

\., j/\'8ER.f~A~ ~:;,;

''cc-C--_(q_~ <7 / '5.)--

CARBONIFEROUS CHART 3

WESTERN EUROPEAN BIOCHRONOLOGIG SCALES EASTERN^AUSTRALIAN^BIOCHRONOLOGIC^SCALES1

COMPOSITE 5ELGIUM/BRITISH ISLES

2AMMONOID^SCALE

s'ag

4CONODONTS

5

BRACHIOPODSG

DISTRIBUTION OF AUSTRALIAN^ANIMON010^SPECIES

coD z0

tu <ILL

-Z LII0coet U)<

U -

>

V3c

____

3 b

BRIGANT-IAN

M y Atea,ai/aceras

C

pz ..I7._a

164 barhylanensis.

.‘Z^.at .,

't k%:!......^...

'`O , \Z3• 6,

'''

..,^ . cfR..k3* • •

GF 6 t'I' . iz,

1 .^8Z■^t^4 t i^k^'t^-,,

: k t^k ^'''3

• 6

^k ■ ^0

p ,

1

cc,ItIzi.,t

t

'Z'i

w,,....""0o6....k,

,--- n .4)*4 0., ...... ,

L' !e^.,..

.'.> .- k t,.^:;--.- $^-`'t$AL^Z t‘k,^•z,l'''-1t •g " ...k^.,0o • Z •...0^LI^•

,^,,^,....,

k^-.^T• •^?

.1

:.•

•

• •

? •^s_ ina -\

i • 2

l'4., 1 ‘kz , 4-, ..x

0Ziite,

•

.,)Zi

4,...80

AO• 5,Z4•• • • • • •^g.

i

^

.....^,^.z.^`")^<^.^I::^4 ^JZ^E^E^‘': — :,,^s' ^,̀,t `4^'4^t i !''

^

: 2 I^'^1 8-•,1'^0" t^i, t^t !

^1 . 4 - 0^j^,..;^t^•^ci .,^glP'"gl:g1^v ^$ 0 -h° 4 .4 ."' IL" i 4Z-eFel-lz-6‘gz."

^

'l2.^4' 32 A ; A^,,,3i

i

1

ir1/3____

MCC,

iTi

Ganiafiles

clc

PI T7•

a

ASG1AN Bar,ahoceta,s

bB 2 —

a 15

___

14

B 1

3

AvrAirauscula

eZ

80//andiles -Bollo/X/OCC,OS

GF 10VS c*

V2 b

=MAN

G F9 13 k.....b....9.....

_t3)

L'/',6

eleyeins

V2 a

Vlb

UNDIANGF8

12

—

11

2

Vi a CHADIAN Li I' irscpc,49,a4 _

AnnoneMpsdas

GF7 10

? amslredis

?

)- z-I <Do -.3 ID

Lu <

zn0

cTn -3 b

-a

IVORIAN

E w

'Fig

GF 5 9 ,zncharoAs .,,

0e

-e^_

3h,....

,,) _

GF48

- - -6

7

Gwlhadussp. A

?

MA Che//ocer-as GF3 sem:/://a5e,

cTn -2 b

a—

ml b

HASTARLANMaensieracetas Gp 2

6U onaraketa

Isomicha -so/

L awv.//afa

Aefluiste-oleiiI1- Gathimlarlia G F 1saRediely,ai,pbrair,see/ceder

COLUMN REFERENCESI. Conil eta/. 1976

Geoese efal,1976Raproth ea/,1983

2. Romsboner• Saunders,I984 3. Manet,1974 4. Jenkins,I914^5. Roberts,1975Riley, 990^ Nory &Crane,1982Riley, 991^ Jenkins etal.,(in press)

G. Campbell eiat, 1983

Carpi/ea' if,9/ by Jones, &HTDraav,^.814R